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New Late Vendian Palaeogeography of Baltica and the TESZ

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New Late Vendian Palaeogeography of Baltica and the TESZ Geological Quarterly, 2004, 48 (4): 309–316 New Late Vendian palaeogeography of Baltica and the TESZ Jerzy NAWROCKI, Andrej BOGUCKIJ and Valentas KATINAS Nawrocki J., Boguckij A. and Katinas V. (2004) — New Late Vendian palaeogeography of Baltica and the TESZ. Geol. Quart., 48 (4): 309–316. Warszawa. New palaeomagnetic poles obtained from the Vendian tuffs and basalts of western Ukraine indicate the necessity of a substantial revision of the Late Vendian–Early Cambrian palaeogeography of the Baltic plate. The palaeopole calculated for the most stable component iso- lated from the Vendian tuffs and basalts is far away from the Vendian–Cambrian apparent polar wander path (APWP), constructed on the basis of Scandinavian poles but is very close to the pole recently isolated from the Vendian sediments of the White Sea Region. Depend- ing on the polarity of the newly-determined Late Vendian pole, two palaeogeographic models of the Baltic plate in the Late Vendian–Early Cambrian are possible. In our preferred model the Baltic plate moved at that time from the moderate southern latitudes to the equator rotating anticlockwise of ca. 120o. This reconstruction explains the geological structures of the marginal zones of Baltica better than the previously proposed stationary model of the Late Vendian–Cambrian Baltica. According to the new late Vendian palaeogeographic scenario, the European, passive margin of Baltica was separated from an active, Avalonian margin of Gondwana. The Late Neoproterozoic tectonic structures of the Brunovistulian Terrane and the Ma³opolska Block were developed near the present day southwestern corner of Baltica that was tectonically active at that time. Alternative reconstruction shows the Baltic plate moving from the moderate northern latitudes in the Vendian, crossing palaeoequator in the latest Vendian, and reaching moderate southern palaeolatitudes in the Late Cambrian. This model, however, would have required exceptionally high plate velocity (ca. 33 cm/year). Jerzy Nawrocki, Polish Geological Institute, Rakowiecka 4, PL-00-975 Warszawa, Poland; e-mail: [email protected]; Andrej Boguckij, Deptartment of Geography, Lvov University, Doroszenki 41, 290000 Lvov, Ukraine; Valentas Katinas, Institute of Geology and Geography, ev¹enkos St. 13, LT-2600 Vilnius, Lithuania (received: July 7, 2004; accepted: November 3, 2004). Key words: Baltica, Ma³opolska, Brunovistulian, Vendian, palaeogeography, palaeomagnetism. INTRODUCTION ern Poland, this domain consists of at least three fault-bounded crustal units. From the margin of Baltica outwards, these are the £ysogóry, the Ma³opolska and the Brunovistulian (Fig. 1). The Brunovistulian was one of the first tectonic units of Central Eu- Since the new palaeomagnetic poles for 535 and 500 Ma rope to be defined as a “terrane” (Brochwicz-Lewiñski et al., were reported, the drift history of Baltica in the Late 1986) and still remains the best-documented terrane of the cen- Vendian–Cambrian has appeared to be well recognized tral part of TESZ (Po¿aryski, 1991; Dadlez, 1995; Franke, (Torsvik and Rehnström, 2001). On the basis of this data and 1995; Pharaoh, 1999). The basement of this terrane is com- the Vendian palaeopoles from the Fen complex (Piper, 1988; posed of metamorphic and igneous rocks, mostly Cadomian Meert et al., 1998), only a minor mobility of the Baltic plate for (Neoproterozoic) in age (Dudek, 1980; Van Breemen et al., 555 to 500 Ma timespan has been proposed (e.g. Hartz and 1982; Finger et al., 2000; ¯elaŸniewicz et al., 2001). In some Torsvik, 2002). In the reconstruction by Hartz and Torsvik places they are covered by the Vendian flysh sequences meta- (2002), Baltica is located between 30° and 60° of southern lati- morphosed in a greenschist grade (¯elaŸniewicz et al., 2001). tude, with its present SW edge facing to the north. This model The Late Vendian metamorphosed flysh sequences cover also does not explain, however, some tectonic problems like the the Ma³opolska Tectonic Block (¯elaŸniewicz, 1998). Because presence of a Cadomian orogen in the basement of the tectonic of these orogenic features, it is difficult to accept any blocks situated near the present SW edge of Baltica. Neoprotorozoic palaeogeography with the Ma³opolska and The present SW margin of Baltica is bordered by a crustal Brunovistulian in the passive margin of Baltica as is presented domain, named the Trans-European Suture Zone (TESZ), by Hartz and Torsvik (2002). Lewandowski (1993) locates the which separates the Precambrian crust of this plate from the Ma³opolska Block near the present southern margin of Baltica Variscan and Alpine mobile belts of western Europe. In South- 310 Jerzy Nawrocki, Andrej Boguckij and Valentas Katinas A certain modification of Baltica palaeogeography has been recently proposed by Lewandowski and Abrahamsen (2003), who situated this continent in the more equatorial posi- tion in the Early Cambrian. New palaeomagnetic studies con- cerning the Vendian sediments of White Sea Region (Popov et al., 2002) disclosed a new palaeopole that is not concordant with the coeval Scandinavian palaeopoles. Any new palaeo- magnetic pole may, therefore, potentially clarify the problem of palaeogeography of Baltica at the turn of the Vendian and Cambrian. For this reason we decided to undertake a palaeo- magnetic study of Late Vendian and Early Cambrian rocks from Ukraine and Estonia. NEW PALAEOMAGNETIC RESULTS MATERIAL AND METHODS Two exposures of the Vendian extrusives from the Volhynia region of the Western Ukraine were sampled for palaeomagnetic investigations. The samples were drilled from the doleritic parts of two lava flows of the pillar basalts croping out in the Bazaltovoye-5 quarry (25 samples), and from dolerit- ic parts of the layered basalts and underlaing tuffs in the Rafalivka quarry (35 samples, see Fig. 1). Sampling was con- strained to three lava flows and one layer of tuffs. All sampled rocks are attributed to the Ratno Beds that compose the upper- most part of the volcanogenic Volhynian Series (Bia³owolska et al., 2002). The Ratno Beds extend as far as SE Poland, where they form uppermost part of the S³awatycze Series (a counter- part of the Volhynian Series). Compston et al. (1995) obtained U-Pb age of 551 ± 4 Ma from the uppermost tuffs of the S³awatycze Series (Fig. 1B). Hence, basalts and tuffs from Bazaltovoye-5 and Rafalivka should be very close to this age. It is unlikely that they are much older than 551 Ma. The Lower Cambrian red mudstones of the Baltija Group were sampled in Kunda quarry (NE Estonia), where 15 hand samples were taken. These rocks are correlated with the Manykayan stage (Paskievicius, 1997). The Vendian sediment, adjanced to the studied Volhynian intrusives dips 3° to the west. The Lower Cambrian sediments from Kunda quarry dip 2° to SW. Vendian samples were subjected to both alternating field (AF) and thermal demagnetization experiments. For Early Cambrian red beds we used thermal demagnetization only. De- Fig. 1. A — location of the studied outcrops within a tectonic sketch map of magnetization results were analysed using orthogonal vector the Central Europe (CDF — Caledonian deformation front, PTB — plots (Zijderveld, 1967), and the directions of the linear seg- Pomerania Tectonic Block, LTB — £ysogóry Tectonic Block, MTB — Ma³opolska Tectonic Block, BVT — Brunovistulian Terrane); B — strati- ments were calculated using principal component analysis graphic subdivision of Vendian–Cambrian sediments from the (Kirschvink, 1980). Magnetic mineralogy was determined with Lublin–Volhyn part of the East European Craton (after Poprawa and the use of isothermal remanent magnetization (IRM) Paczeœna, 2002); location of studied exposures Bazaltovoye-5 and techniques and thermomagnetic analyses. Rafalivka is marked with circles in the Early Palaeozoic. He postulates a large-scale tectonic RESULTS OF DEMAGNETIZATION transport of the Ma³opolska to its present position during the Variscan orogeny. However, the palaeomagnetic pole obtained Most of the samples from the Volhynia revealed a from the Bardo diabase (S part of the Holy Cross Mts., low-coercivity natural remanent magnetization (NRM) compo- Ma³opolska Block) indicates that such a movement could not nent, removed by alternating fields up to 20 mT and tempera- take place after the Silurian (Nawrocki, 2000). tures of about 350°C (Fig. 2). In the samples from Rafalivka this component was strongly dispersed and therefore was not New Late Vendian palaeogeography of Baltica and the TESZ 311 Fig. 2. Typical demagnetization characteris- tics (orthogonal plots, intensity decay curves and demagnetization directional tracks) of Vendian basalts and tuffs from Rafalivka and Bazaltovoye-5 quarries, and Lower Cam- brian mudstones from Kunda quarry Circles in the orthogonal plots represent ver- tical projections, squares represent horizontal projections; the characteristic components “A”, “B”, “C1” and “C2” are marked on the orthogonal plots; Irm — intensity of remanent magnetization, Inrm — initial in- tensity of natural remanent magnetization intesity, “B” magnetization usually fluctuated at the last levels of demag- netization. Samples from the Lower Cam- brian red mudstones revealed the presence of a one distinct component “C2”. This magnetization was de- finedintemperaturesupto550°C, as a straight-line segment not directed towards the origin in orthogonal pro- jection (Fig. 2). These rocks also con- tained a high temperature compo- nent. Its credible definition was im- possible because
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